Sequence Stratigraphy of the Neoproterozoic Infra Krol Formation and Krol Group, Lesser Himalaya, India

Jiang, Ganqing; Christie‐Blick, Nicholas; Kaufman, Alan J.; Banerjee, D. M.; Rai, Vibhuti

doi:10.1306/120301720524

Cited by 109 publications

(68 citation statements)

References 69 publications

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“…Whether or not those ancient deposits were exposed to the same degree of freshwater alteration as Clino is still a matter of debate 28 . In many cases, negative d 13 C carb excursions have been interpreted to be pristine records of global carbon cycling 15,[19][20][21]56,57 , because sedimentological evidence of subaerial exposure was not observed 26,58 . However, subaerial exposure surfaces can be cryptic in the rock record, and other workers have interpreted the same geochemical changes to be diagenetic in origin 28,59 .…”

Section: Article Nature Communications | Doi: 101038/ncomms5672mentioning

confidence: 99%

Interpreting carbonate and organic carbon isotope covariance in the sedimentary record

2014

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Many negative d 13 C excursions in marine carbonates from the geological record are interpreted to record significant biogeochemical events in early Earth history. The assumption that no post-depositional processes can simultaneously alter carbonate and organic d 13 C values towards more negative values is the cornerstone of this approach. However, the effects of post-depositional alteration on the relationship between carbonate and organic d 13 C values have not been directly evaluated. Here we present paired carbonate and organic d 13 C records that exhibit a coupled negative excursion resulting from multiple periods of meteoric alteration of the carbonate d 13 C record, and consequent contributions of isotopically negative terrestrial organic matter to the sedimentary record. The possibility that carbonate and organic d 13 C records can be simultaneously shifted towards lower d 13 C values during periods of subaerial exposure may necessitate the reappraisal of some of the d 13 C anomalies associated with noteworthy biogeochemical events throughout Earth history.

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Section: Article Nature Communications | Doi: 101038/ncomms5672mentioning

confidence: 99%

Interpreting carbonate and organic carbon isotope covariance in the sedimentary record

2014

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“…The balance of evidence thus indicates that Doushantuo-Pertatataka acritarchs may have gone extinct either before or at the Gaskiers glaciation (Zhou et al 2001a;. If so, then the large negative d 13 C extinction (EN3) in the East Yangtze Gorges area and its potential equivalents-the Shuram negative excursion in Oman (Burns and Matter 1993;Le Guerroue et al 2006), the Wonoka negative excursion in the Adelaide Rift Complex (Calver 2000) and possibly the Krol B/C negative excursion in Lesser Himalaya (Jiang et al 2002;Kaufman et al 2006)-must have lasted ca. 30 million years, because the EN3 started below the last occurrence of Doushantuo-Pertatataka acritarchs ( Figure 2) and ended about 551.1 AE 0.7 Ma .…”

Section: The Extinction Of Doushantuo-pertatataka Acritarchsmentioning

confidence: 99%

The diversification and extinction of Doushantuo‐Pertatataka acritarchs in South China: causes and biostratigraphic significance

et al. 2006

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The Ediacaran Period immediately follows the last Cryogenian glaciation-the $635 Ma Marinoan or Nantuo glaciation, and it is also punctuated by another brief glaciation-the $582 Ma Gaskiers glaciation. It is possible that these glaciations may have had significant impact on Ediacaran biological evolution (e.g. the appearance or disappearance of Doushantuo-Pertatataka acritarchs). Alternative hypotheses propose that the diversification of Doushantuo-Pertatataka acritarchs was caused by the Acraman bolide impact or by emerging eumetazoans. To test these hypotheses, high-resolution geochronological and biostratigraphic data are required. The Doushantuo Formation in South China, radiometrically constrained between $635 and $551 Ma, has the potential to clarify the global picture of early-middle Ediacaran evolution. Here we present preliminary biostratigraphic data from the Doushantuo Formation in the East Yangtze Gorges area and new d 13 C chemostratigraphic data from the Doushantuo Formation at Weng'an. These and previously published palaeontological data, aided by the tool of d 13 C chemostratigraphy, indicate that the biostratigraphic record of the Doushantuo Formation is locally sensitive to the availability of specific taphonomic windows. In the East Yangtze Gorges area, Doushantuo-Pertatataka acritarchs first appeared shortly after the termination of the Nantuo glaciation and gradually diversified throughout the Doushantuo Formation. At Weng'an, however, such acritarchs first appear-abruptly and in much greater diversity-in phosphorite of the upper Doushantuo Formation, immediately above a subaerial exposure surface. Thus, the biostratigraphic pattern in the East Yangtze Gorges area permits, whereas that at Weng'an apparently disallows, a causal relationship between the Nantuo glaciation and the diversification of Doushantuo-Pertatataka acritarchs. We conclude that the biostratigraphic record is incomplete at Weng'an, where the early Ediacaran evolutionary history is not preserved. The South China data indicate that special attention has to be paid to taphonomic and palaeoenvironmental analysis before extrapolating local and regional biostratigraphic ranges to make global interpretations.It is less clear when Doushantuo-Pertatataka acritarchs disappeared. Previous investigators have variously suggested that they disappeared before, at, or after, the Gaskiers glaciation. These hypotheses are difficult to test because of the lack of sedimentary evidence for the Gaskiers glaciation in South China and other regions (e.g. South Australia) where Doushantuo-Pertatataka acritarchs are abundant. In Australia, Doushantuo-Pertatataka acritarchs are thought to have experienced a sharp decline after the Egan glaciation, which may well be equivalent to the Gaskiers glaciation. If true, then Doushantuo-Pertatataka acritarchs are largely restricted to the interval between the Nantuo and Gaskiers glaciations. This conclusion allows us to place constraints on the possible causes of the diversification and extinction of Doushant...

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“…Lithologies of sections are greatly simplified and no thicknesses are implied. Sections: Siberia: absolute date from Bowring et al (1993), stratigraphy after Knoll et al (1995), Pelechaty et al (1996), and Pelechaty (1998); Namibia: absolute dates from Grotzinger et al (1995), stratigraphy after Saylor et al (1998) and Saylor (2003) and references therein; India: stratigraphy and preliminary isotopic data from Jiang et al (2002); Southeast USA: Nd = Noonday Dolomite, sequence stratigraphy after Fedo and Cooper (2001), stratigraphy and chemostratigraphic data after Corsetti and Hagadorn (2000) and Prave (1999); Mackenzie Mountains: Rt = Ravensthroat cap carbonate, BBR = Backbone Ranges Formation, stratigraphy and sequence boundaries after Narbonne and Aitken (1995), MacNaughton et al (2000) and Dalrymple and Narbonne (1996); isotopic trends after Narbonne et al (1994) and Kaufman et al (1997); Wernecke Mountains based on this present study, BBR-V = Backbone Ranges-Vampire Formation.…”

Section: Intrabasinal Sequence Stratigraphic Correlationmentioning

confidence: 99%

“…Comparison is drawn with mixed siliciclastic-carbonate successions that have similarly integrated chronostratigraphies. These include differing tectonic regimes such as the intracratonic-basin setting of Siberia (Pelechaty, 1998), foreland basin of Namibia (Saylor et al, 1998), and passive margin settings of India (Jiang et al, 2002), the southern Cordillera (Corsetti and Hagadorn, 2000) and northwestern Canada (Fig. 10).…”

Section: Global Correlationsmentioning

confidence: 99%

“…Dates from Namibia suggests the duration of the invariant and N sC intervals may be 5-6 million years (Saylor et al, 1998). There are a varying number of sequence boundaries at this level in Namibia (Saylor et al, 1998) and India (Jiang et al, 2002), of both interpreted tectonic and eustatic nature, which hinders the linkage of these surfaces. SB 2 and its correlative surface in the Mackenzie Mountains lie in a position immediately above the positive interval.…”

Section: Global Correlationsmentioning

confidence: 99%

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Integrated Ediacaran chronostratigraphy, Wernecke Mountains, northwestern Canada

Pyle

Narbonne

James

et al. 2004

Precambrian Research

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Terminal Neoproterozoic (Ediacaran, ca. 600-543 Ma) strata of the upper part of the Windermere Supergroup are well-exposed in the Mackenzie Mountains and the Wernecke Mountains of northwestern Canada. Windermere strata in the Mackenzie Mountains contain an exceptional Ediacaran biostratigraphic and isotopic (C and Sr) record, while the sequence stratigraphic record is subtle throughout this predominantly deep-water succession. Coeval strata in the Wernecke Mountains can be correlated with the succession in the Mackenzie Mountains on a formational level. In contrast to the deep-water setting of the Mackenzies succession, the Werneckes succession preserves a predominantly shallow-water succession amenable to detailed sequence stratigraphy. Integrated lithostratigraphy, chemostratigraphy, biostratigraphy and sedimentology partitions the Wernecke Mountains succession into five depositional sequences and constrains correlation with strata in the Mackenzie Mountains. The siliciclastic and carbonate sediments, deposited along the margin of the proto-Pacific Ocean, record accumulation in continental slope, neritic, and terrestrial paleoenvironments. Distinctive temporal chemostratigraphic and biostratigraphic attributes allow these strata to be correlated with other Ediacaran successions worldwide. Integrating sequence stratigraphy with these attributes is a robust, yet under-utilized correlation tool and is a step toward erecting a more detailed working Neoproterozoic chronostratigraphy.

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Sequence Stratigraphy of the Neoproterozoic Infra Krol Formation and Krol Group, Lesser Himalaya, India

Cited by 109 publications

References 69 publications

Interpreting carbonate and organic carbon isotope covariance in the sedimentary record

Interpreting carbonate and organic carbon isotope covariance in the sedimentary record

The diversification and extinction of Doushantuo‐Pertatataka acritarchs in South China: causes and biostratigraphic significance

Integrated Ediacaran chronostratigraphy, Wernecke Mountains, northwestern Canada

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